ORIGINAL PAPER

Assessment of the Tectonic Activity in Northwestern Partof the Zagros Mountains, Northeastern Iraq by UsingGeomorphic Indices

Ziyad Elias . Varoujan K. Sissakian . Nadhir Al-Ansari

Received: 14 February 2019 / Accepted: 26 March 2019 / Published online: 8 April 2019

� The Author(s) 2019

Abstract The Tectonic Activity of regions with

active tectonics can be assessed by using of the

geomorphic indices. Six Geomorphic indices includ-

ing stream-gradient index (SL), drainage basin asym-

metry (Af), drainage basin shape (Bs), hypsometric

integral (Hi), valley floor width-valley height ratio

(Vf), and mountain-front sinuosity (Smf) were calcu-

lated using GIS technique in Kifri Chai Basin;

northeast Iraq, which belongs to the Western Zagros

Mountain. The basin was divided into eighteen sub-

basins depending on the 4th, 5th and 6th stream orders

of the drainage within Kirfi Basin. It was found that the

SL, Af, Bs, Hi, Vf, and Smf (J) values are uniform and

exhibit almost the same classes. However, few

exceptions occur, especially in Bs values, but the

exceptional values do not influence significantly on

the acquired results, in each of the eighteen sub-basin.

From these indices the relative active tectonics index

value (Iat) was determined. The results of average Iat

values (2.35) showed that the tectonic activity in the

whole basin is Moderate. Moreover, an attempt was

carried out to compare the regional Neotectonic

activity with the relative tectonic activity in the basin.

The results showed that there is a positive relation

between the two comparatives; especially the subsi-

dence amount and scored relative tectonic activity.

Keywords Geomorphic indices � Tectonic activity �Neotectonic � Western Zagros � Iraq

1 Introduction

The phenomenon of tectonic movements is the best

recognized in the history of basin development.

Therefore, landscape analyses of such areas and

studies of drainage networks, in particular, provide

insights into current tectonic processes and their

activities. Attempts to quantify tectonic deformation

from landscape analyses have been performed for

decades (e.g., Bull and McFadden 1977; Rockwell

et al. 1985; Merritts and Vincent 1989; Burbank 1992;

Burbank and Anderson 2001; Keller and Pinter 2002;

Crosby and Sheehan 2006; Wobus et al. 2010, 2012;

Kirby and Whipple 2012). The rapid development of

GIS techniques and the constant advancement in

Z. Elias

Geomorphic Researcher, Hannover, Germany

e-mail: ziyadelias@yahoo.com

V. K. Sissakian

University of Kurdistan, Hewler, KRG, Iraq

e-mail: f.kajeek@ukh.edu.krd;

varoujan49@yahoo.com

V. K. Sissakian

Private Consultant Geologist, Erbıl, Iraq

N. Al-Ansari (&)

Lulea University of Technology, Lulea, Sweden

e-mail: Nadhir.alansari@ltu.se

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https://doi.org/10.1007/s10706-019-00888-z(0123456789().,-volV)(0123456789().,-volV)

digital elevation model (DEM) quality and access

provide significant and efficient tools to compute,

calculate and analyze geomorphic indices across areas

of various environments and scales (e.g., Keller et al.

1982; Ramırez-Herrera 1998; Kirby et al. 2003;

Gurbuz and Gurer 2008; Arrowsmith and Zielke

2009; Gasparini andWhipple 2014). However, studies

that use geomorphic indices to explore the relative

activity of tectonic processes in the fore-arc regions of

active subduction zones are limited and/or use only

one or two indices (e.g., Wells et al. 1988; Fisher et al.

1998; Morell et al. 2008; Rehak et al. 2008).

Active deformation in the Zagros Mountains is

caused by the northward motion of the Arabian Plate

with respect to Eurasian Plate, which occurs at a rate of

25 mm year -1 at longitude 56�E (Ramsey et al.

2008). The style of deformation appears to vary along

the strike of the Zagros Mountain Range. In the NW

(Dezful), N–S shortening between Arabia and Eurasia

plates is accommodated on a spatially separated

system of NW trending right-lateral strike–slip and

thrust faults (Ramsey et al. 2008). It is worth to

mention that Dezful Embayment in Iraq is called

Kirkuk Embayment (Fouad 2012).

Recent works have been carried out on the tectonic

activity; among them are Verrios et al. (2004), they

performed their study in Greece. El-Hamdouni et al.

(2008) performed their study in South of Spain. In Iran

many studies were performed, Ghassemi (2005) has

commented on the fold growth in NE Alborz, Dehbo-

zorgi et al. (2010) in central Zagros Range, Mumipour

and Najad (2011) in south of Iran, Toudeshki and

Arian (2011) in northwest Iran, Habibi and Gharibreza

(2015) in central part of Iran, and Mosavi and Arian

(2015) in northeast of Iran. All those studies have used

the geomorphological indices to indicate the tectonic

activity in their studied areas.

The above mentioned review for a part of the

existing literature indicates that the knowledge about

the effects of tectonic movements upon river valley

forms; fluvial processes are not sufficiently investi-

gated in the Iraqi territory where these issues are very

rarely studied and require more detailed studies.

Kfiri Chai Basin is located in the north-eastern part

of Iraq (Fig. 1). The coverage area is 2821.15 km2.

The Kifri Chai Basin was divided into eighteen sub-

basins and called them in this study as Sub-basins No.

1 to No. 18.

The main aim of the current study is to indicate the

tectonic activity of Kifri Chai Basin which is part of

the Western Zagros Range. Moreover, the relative

tectonic activity was compared with the regional

Neotectonic movements in Kifri Chai Basin to indi-

cate the relation between both aspects.

1.1 Geological and Neotectonic Setting

The studied area is located within the Low Folded

Zone of the Outer Platform, which belongs to the

Arabian Plate (Fouad 2012). Four anticlines occur in

the study area; these are from the north to south: Kalar,

Pulkhana, Qumar and Gillabat (Fig. 2).

All the anticlines exhibit thrusting, where their

northeastern limbs are thrusted over their southwestern

limbs causing their disappearance and the anticlinal

axis (Sissakian 1978; Youkhanna andHradecky 1978).

The youngest exposed formation is the Bai Hassan

Formation. This means that the thrusting had occurred

after the Middle Pleistocene; accordingly, it is consid-

ered as a neotectonic movement (Obruchev 1948).

The exposed formations in the Kifri Chai Basin are:

1. Fatha Formation (Middle Miocene): Consists

mainly of reddish brown claystone, marl, lime-

stone and gypsum and cyclic nature.

2. Injana Formation (Upper Miocene): Consists

mainly of reddish brown sandsotone, siltstone and

claystone in cyclic nature.

3. Mukdadiya Formation (Upper Miocene–Plio-

cene): Consists of greyish sandsotone, siltstone

and claystone in cyclic nature. With some pebbly

sandstone.

4. Bai Hassan Formation (Pliocene–Pleistocene):

Consists mainly of conglomerate, reddish brown

claystone in cyclic nature, with some sandstone

beds.

5. Quaternary sediments: Mainly valley fill, flood

plain and slope sediments, besides river terraces

The neotectonic activity in Iraq is considered since the

Upper Miocene, when the marine environment was

terminated and continental depositional environment

prevailed. This assumption is based on Obruchev

(1948) and Atomenergoexport (1985). Sissakian and

Deikran (1998) compiled the NeotectonicMap of Iraq,

which is based on the contact between the Fatha

Formation (Middle Miocene) and the Injana

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Formation (Upper Miocene) as compared to the

present topography.

1.2 Data Used and Methodology

This study was carried out using Radar Topography

Mission (SRTM) data with extensive use of previously

published geological, and Neotectonic maps. The

borders of the sub- basins were delineated using SRTM

image that has a ground resolution of 3-arc-second

(90 m) and a vertical resolution of approximately 10 m.

Kifri Chai Basin was divided into eighteen sub-

basins according to the ordering of the streams, using

Straller’s streamorderingmethod. The streamorderwas

generated up to 6th orders using the stream ordering

module of ArcGIS. The eighteen sub-basins are located

depending on the 4th, 5th, and 6th stream orders. The

coverage area of the basin was extracted from the DEM

map using the basin extraction tool of ArcGIS which

gives accurate size and shape of each sub basin.

2 Geomorphic Indices

Six geomorphic indices were used to estimate the

relative tectonic activity in Kifri Chai Basin. For each

index, a map was constructed based on DEM image

which shows the classes of each index at each sub-

basin. The measured six geomorphic indices at each

sub-basin are mentioned hereinafter. The acquired

values (Table 1) and classes are according to El-

Hamdouni et al. (2008) and enclosed references.

2.1 Stream-Gradient Index (Sl)

This index shows the relation between the length of a

valley and its gradient, it is defined as:

SL ¼ ðDH=DLÞ � L

where SL denotes the Stream length gradient index,

DH/DL denotes the channel slope or gradient of the

reach (DH is the change in elevation of the reach and

Fig. 1 Location map of the studied area and the 18 sub-basins

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Fig. 2 Geological map of the studied area and near surroundings (After Sissakian and Fouad 2014; Barwary and Slewa 2014a, b)

Table 1 Values of geomorphic indices of the eighteen sub basins

Sub-basin no Stream order Sub basin area (km2) Sl Af Bs Hi Vf Smf

1 6 521.34 90 39.28 2.78 0.14 2.8 2.3

2 5 129.96 160 41.89 2.18 0.16 3.2 1.6

3 5 152.76 220 47.86 5.6 0.19 9.7 1.2

4 5 46.75 49 27.98 2.17 0.10 9.1 *

5 5 105.59 257 59.06 15.96 0.29 7.7 1.2

6 4 274.49 180 48.5 5.5 0.13 2.3 2.4

7 4 220.82 220 36.48 4.96 0.13 2.6 2.2

8 4 204.81 280 46.06 2.83 0.15 2 1.2

9 4 69.15 240 36.22 3.9 0.16 7.2 1.3

10 4 273.75 700 53.75 2.78 0.26 0.9 2.5

11 4 64.51 200 61.74 3.27 0.16 13.9 *

12 4 90.10 280 38.93 2.16 0.22 5.1 1.3

13 4 58.82 200 53.23 2.04 0.12 11.7 1.3

14 4 176.87 800 73.39 5.68 0.28 4.0 2.8

15 4 30.08 160 50.99 3.33 0.11 4.0 1.4

16 4 99.70 400 62.89 5.51 0.25 10.9 2.7

17 4 106.47 140 31.01 2.2 0.08 12.2 1.1

18 4 195.18 1000 50.18 9.18 0.32 8.6 1.9

Average 309.8 47.75 4.56 0.18 6.55 1.8

*No mountain front exists in the sub-basin

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DL is the length of the reach), and L denotes the total

channel length from the point of interest (Hack 1973).

The values of the Sl in the eighteen sub-basins are

assigned in Table 1. The (Sl) Index is classified into

three tectonic activity classes: (Class 1) High

(Sl[ 500), (Class 2) Moderate (300 C Sl\ 500),

and (Class 3) Low (Sl\ 300). The acquired average

Sl value is 309.8 which indicates Class 2, meaning

Moderate tectonic activity, the classes of the eighteen

sub-basins are shown in Fig. 3.

2.2 Asymmetric Factor (Af)

The asymmetric factor (Af) was used to evaluate the

tectonics activity at a drainage basin scale. Its area of

application is relatively large (Hare and Gardner 1985;

Keller and Pinter 2002). The Af index is formulated as

follows:

Af ¼ 100 � Ar=Atð Þ:

where Ar represents the area on the right side of the

trunk stream, and At represents the total area of the

drainage basin.

The values of the Af in the eighteen sub-basins are

assigned in Table 1. The Asymmetric Factor (Af) is

classified into three classes: (Class 1) (Af\ 35 or

Af[ 65), (Class 2) (57\Af\ 65 or 35\Af\ 43),

and (Class 3) (43\Af\ 57). The average Af value is

47.7 which indicates Class 3, and the classes of the

eighteen sub-basins are shown in Fig. 3.

2.3 Basin Shape Index (Bs)

This index indicated the shape of the basin and its

relation with the relative tectonics. This index is

identified as:

Bs ¼ Bl=Bw

where Bl is the length of a basin measured from the

headwaters point to the mouth of the sub basin, and

Bw is the width of sub basin measured at its widest

point.

The basin shape index (Bs) includes three classes:

(Class 1) Elongate basin with Bs[ 4; (Class 2) Semi-

elongate basin with 3 B Bs\ 4; and (Class 3)

Circular basin with Bs\ 3. The values of the Bs in

the eighteen sub-basins are assigned in Table 1. The

average Bs value is 4.56 which indicates Class 1. The

classes of the eighteen sub-basins are shown in Fig. 4.

Fig. 3 Map of the eighteen sub-basins classes. (Left) Stream Gradient Index (Sl), (Right) Asymmetric Factor (Af)

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2.4 Hypsometric Integral (Hi)

The hypsometric integral (Hi) describes the relative

distribution of elevation in a given area of a landscape,

particularly a drainage basin (Strahler 1952). The

index is defined as the relative area below the

hypsometric curve and thus expresses the volume of

a basin that has not been eroded. A simple equation to

approximately calculate the index is (Pike and Wilson

1971; Mayer 1990; Keller and Pinter 2002):

Hi ¼ ðaverage elev:�min: elev:Þ=ðmax: elev:�min: elev:Þ

The Hypsometric Integral index (Hi) is classified

into three classes: (Class 1) (Hi C 0.5), (Class 2)

(0.4 B Hi\ 0.5) and (Class 3) (Hi\ 0.4). (Table 1).

The values of the Hi in the eighteen sub-basins are

assigned in Table 1. The average Hi value is 0.18,

which indicates Class 3. The classes of the eighteen

sub-basins are shown in Fig. 4.

2.5 Ratio of Valley Floor Width to Valley Height

(Vf)

This index gives the ration between the width of the

valley floor and the height of the valley in certain area

within a valley, it is a good indication about the

erosion and tectonic activity. This parameter is

calculated as:

Vf ¼ 2Vfw= Eld � Escð Þ þ Erd � Escð Þ½ �

where Vf denotes the valley floor width to valley

height ratio, Vfw denotes the width of the valley floor,

E ld and E rd stand for elevations of the left and right

valley divides, respectively E sc denotes the elevation

of the valley floor (Keller and Pinter 2002; Cuong and

Zuchiewicz 2001).

The Vf index is divided into three classes: (Class 1)

(VfB 0.5), (Class 2) (0.5 B Vf\ 1.0) and (Class 3)

(VfC 1). The valleys are often narrow upstream from

the mountain front (Ramırez-Herrera 1998). The

indicated values of Vf are assigned in Table 1. The

acquired average Vf value is 6.55 which indicates

Class 3. The classes of the eighteen sub-basins are

shown in Fig. 5.

2.6 Mountain-Front Sinuosity Index (Smf) (J)

The index reflects the balance between erosion forces

that tend to cut embayment into a mountain front and

tectonic forces that tend to produce a straight mountain

front (Verrios et al. 2004).

Mountain front sinuosity index is defined as:

Fig. 4 Map of the eighteen sub-basins classes. (Left) Basin Shape Index (Bs), (Right) Hypsometric Integral (Hi)

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Smf ¼ Lmf=Ls

where Smf denotes the mountain front sinuosity; Lmf

denotes the length of the mountain front along the foot

of the mountain at the pronounced break in slope, and

Ls denotes the straight-line length of the mountain

front.

The values of the J in the eighteen sub-basins are

assigned in Table 1 and the classes are presented in

Fig. 5. The measured mountain-fronts are shown in

Fig. 6. The Mountain Front Sinuosity Index (J) is

divided into three classes: (Class 1) High, J = 1.0 to

1.5, (Class 2) Moderate, J = 1.5 to 2.5, and (Class 3)

Low, J[ 2.5 (El-Hamdouni et al. 2008). The acquired

average Smf value is 1.8 which indicates Class 2.

3 Evaluation of Relative Tectonic Activity (Iat)

We have used the average of the six measured

geomorphic indices to indicate the relative tectonic

activity (Iat), following El-Hamdouni et al. (2008).

This index represents a summary and average of the

given geomorphic indices, it is calculated as follows

(Habibi and Gharibreza 2015):

Iat ¼ S=N,

where S represents the sum of previous indices, N

represents the number of selected indices.

The values of the Iat index are divided into four

classes (El-Hamdouni et al. 2008) to define the degree

of active tectonics: Class 1—Very high (1.0 B Iat\1.5), Class 2—High (1.5 B Iat\ 2.0), Class 3—

Moderate (2.0 B Iat\ 2.5), and Class 4—Low

(Iat[ 2.5). The Iat values in the eighteen sub-basins

range from 2.00 to 2.66 and the average Iat value is

2.35 (Table 2), which indicates Class 3; meaning

Moderate tectonic activity. The Iat classes of the

eighteen sub-basins are presented in Fig. 6.

4 Relation Between Regional Neotectonic Activity

and Local Tectonic Activity

The Kifri Chai Basin represents the deepest subsided

areas within the whole Zagros Foreland Basin inside

the Iraqi territory. The depth of the Middle–Upper

Miocene contact reaches up to 3000 m below the sea

level (Table 3 and Fig. 7). However, the maximum

up-warped reaches 250 m (a.s.l.) and the Zero Line

(Fig. 7) which represents the Middle–Upper Miocene

sea level runs in the middle part of the basin.

Fig. 5 Map of the eighteen sub-basins classes. (Left) Ratio of Valley Floor Width to Valley Height (Vf), (Right) Mountain-front

sinuosity index (Smf)

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Fig. 6 (Left) The measured Mountain Fronts (J) within the eighteen sub-basins, (Right) Map of Relative Tectonic Activity (Iat)

Classes of the eighteen sub-basins

Table 2 Classes of the geomorphic indices with Iat values and classes, and tectonic activity of the eighteen sub-basins

Sub-basin no Stream order Sl Af Bs Hi Vf Smf Lat Tectonic activity

Class Value Class

1 6 3 2 3 3 3 2 2.66 4 Low

2 5 3 2 3 3 3 2 2.66 4 Low

3 5 3 3 1 3 3 1 2.30 3 Moderate

4 5 3 1 3 3 3 * 2.15 3 Moderate

5 5 3 2 1 3 3 1 2.16 3 Moderate

6 4 3 3 1 3 3 2 2.50 3 Moderate

7 4 3 2 1 3 3 1 2.16 3 Moderate

8 4 3 3 3 3 3 1 2.66 4 Low

9 4 3 2 2 3 3 1 2.30 3 Moderate

10 4 1 3 3 3 2 2 2.30 3 Moderate

11 4 3 2 2 2 3 * 2.16 3 Moderate

12 4 3 2 3 3 3 1 2.50 3 Moderate

13 4 3 3 3 3 3 1 2.60 4 Low

14 4 1 1 1 3 3 3 2.00 2 High

15 4 3 3 2 3 3 1 2.50 3 Moderate

16 4 2 2 1 3 3 3 2.30 3 Moderate

17 4 3 1 3 3 3 1 2.30 3 Moderate

18 4 1 3 1 3 3 2 2.16 3 Moderate

Average 2.66 2.20 2.05 2.94 2.94 1.56 2.35 3 Moderate

*Means there is no Mountain Front in the sub-basin

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Table 3 Neotectonic data and Iat values of the 18 sub-basins within Kifri Chai Basin

Sub-

basin

No.

Neotectonic activity (12 Ma) Neotectonic activity during Iat Tectonic

ActivityPleistocene (2.8 Ma) Holocene (11.7 ka)

Subsidence Upward Subsidence Upward Subsidence Upward Value

Rate (cm/100 years) Amount (m) Amount (m) Class

Min. Max. Min. Max. Min Max Min Max Min Max Min Max

1 1000 1500 * * 7.18 11.64 * 0.98 1.47 * 2.66 L

0.84 1.26 4

2 1500 * * 11.64 * 1.47 * 2.66 L

1.26 4

3 1000 1500 * * 7.18 11.64 * 0.98 1.47 * 2.30 M

0.84 1.26 3

4 2000 2500 * * 15.52 19.40 * 1.96 2.45 * 2.16 M

1.66 2.10 3

5 2500 * * 19.40 * 2.45 * 2.16 M

2.10 3

6 750 1500 * * 5.82 11.64 * 0.73 1.47 * 2.50 M

0.63 1.26 3

7 1000 1500 * * 7.18 11.64 * 0.98 1.47 * 2.16 M

0.84 1.26 3

8 1000 2500 * * 7.18 19.40 * 0.98 2.45 * 2.66 L

0.84 2.10 4

9 2000 2500 * * 15.52 19.40 * 1.96 2.45 * 2.30 M

1.66 2.10 3

10 0 2000 0 250 0 15.52 0 1.94 0 1.96 0 0.24 2.30 M

0 1.66 0 0.21 3

11 2000 3000 * * 15.52 23.28 * 1.96 2.93 * 2.16 M

1.66 2.50 3

12 0 500 0 250 0 3.88 0 1.94 0 0.49 0 0.24 2.50 M

0 0.42 0 0.21 3

13 2000 2500 * * 15.52 19.40 * 1.96 2.45 * 2.60 L

1.66 2.10 4

14 0 2500 0 250 0 19.40 0 1.94 0 2.45 0 0.24 2.00 H

0 2.10 0 0.21 2

15 3000 * * 23.28 * 2.93 * 2.50 M

2.50 3

16 0 2500 0 250 0 19.40 0 1.94 0 2.45 0 0.24 2.30 M

0 2.10 0 0.21 3

17 2500 3000 * * 19.40 23.28 * 2.45 2.93 * 2.30 M

2.10 2.50 3

18 0 2500 0 250 0 19.40 0 1.94 0 2.45 0 0.24 2.16 M

0 2.10 0 0.21 3

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The amounts and rates of the subsidence and/or

upward movements, during the Neotectonic Period,

and the Iat values and tectonic activity class in each of

the eighteen sub-basins are assigned in Table 3.

Moreover, the subsidence and upwards amounts were

calculated during the Pleistocene (2.8 Ma) and the

Holocene (11.7 Ka) (ICS 2012) in the eighteen sub-

basins (Table 3). The amount of the subsidence during

the Neotectonic period, Pleistocene and Holocene

range from (0–3000), (0–23. 28) to (0–2.93) m,

respectively. Whereas the amount of the upward

movement during the three intervals range (0–250),

(0–1.94) and (0–0.24) m, respectively. The subsidence

Table 3 continued

Sub-

basin

No.

Neotectonic activity (12 Ma) Neotectonic activity during Iat Tectonic

ActivityPleistocene (2.8 Ma) Holocene (11.7 ka)

Subsidence Upward Subsidence Upward Subsidence Upward Value

Rate (cm/100 years) Amount (m) Amount (m) Class

Min. Max. Min. Max. Min Max Min Max Min Max Min Max

Average 1125 2166 0 69.44 9.463 15.522 0 0.538 1.21 2.58 0 0.067 2.35 M

0.937 1.805 0 0.578 3

Bold indicates the rate or subsidence or upward movements (cm/100 years)

The recorded upward and downward movements are in meter

*Means no upward movement

H high, M moderate, L low

Fig. 7 Neotectonic map of the studied four sub-basins. (Modified from Sissakian and Deikran 1998). The background is Sentinel

image

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and upward rates during the Neotectonic period range

(0–2.5) and (0–0.21) cm/100 year, respectively.

Those sub-basins which exhibit wide range of

subsidence, the Iat values indicate High tectonic

activity (Sub-basin No. 14) or Medium tectonic

activity, but with Iat value of 2.16 which is very close

to Class 2 (for example Sub-basin No. 18).

The subsidence amount depends on the thickness of

the exposed formations younger than the Fatha

Formation which forms the beginning of the Neotec-

tonic phase in Iraq. The thicknesses of the Injana,

Mukdadiya and Bai Hassan formations which overlie

the Fatha Formation are considered in the construction

of the Neotectonic map of Iraq (Sissakian and Deikran

1998). The thicknesses are highly variable in the area;

therefore, any miss-estimation of the thicknesses will

give subsidence wrong amount of subsidence. This

may be the case with Sub-basin No. 4.

5 Results

The acquired data of the six studied geomorphic

indices showed that the average Iat value in Kifri Chai

Basin is 2.35, which means Class 3; meaning that the

Relative Tectonic Activity in the basin is Moderate

(Table 2). Moreover, the regional Neotectonic activity

data showed that there is positive relation with the

relative tectonic activity in Kifri Chai Basin.

6 Discussion

The tectonic activity and the values of each of the six

geomorphic indices are discussed showing the main

differences and the reasons for similarities and/or

anomalous results within the eighteen sub-basins. The

average value of tectonic activity indicator (Iat) in the

eighteen sub-basins is 2.35 (Tables 2, 4), which

indicates Class 3 and means that the tectonic activity

is Moderate. Accordingly, the tectonic activity of Kifri

Chai Basin is Moderate.

The prevalence of the Medium tectonic activity in

Kifri Chai Basin (Tables 2, 3, 4, and Fig. 6, Right) is

attributed to the following reasons: (1) The exposed

rocks within the eighteen sub-basins are mainly

clastics, with exception of the Fatha Formation, which

includes gypsum and limestone beds with thick

claystone beds and thin sandstone beds. Although

the Fatha Formation is exposed only in Sub-basins No.

5, 8, 9 and 10 and a very small part in Sub-basin No. 11

(Fig. 2), but the coverage area is very small, along the

thrust of Pulkhana anticline only (Fig. 2); therefore,

the presence of both rock types does not affect

significantly the geomorphological indices as com-

pared to the clastic rocks which cover the majority of

the basin, (2) Tectonically, the eighteen sub-basins are

located within the Low Folded Zone (Fouad 2012);

therefore, have influenced by the same tectonic

stresses during the past geological time, (3) The

average of the Mountain Front index values is 1.8

(Tables 1, 2), whichmeansModerate class, but, within

Sub-basins No. 3, 5, 8, 9, 12, 13, 15 and 17 is High

Class (Table 1). This means in those sub-basins the

tectonic activity was higher. Otherwise the Mountain

Front index value wouldn’t be High, (4) The eighteen

sub-basins are covered mainly by clastic rocks (Sis-

sakian and Fouad 2014, Barwary and Slewa 2014a, b),

and are under the same climatic conditions, as the

annual rain fall and temperature are concerned;

therefore, the shape, size and orders of the valleys

are almost the same. Accordingly, the SL, Af, Bs, Hi

and Vf values (Table 1) are uniform and exhibit

almost the same classes. However, few exceptions

Table 4 Statistical data about the classes of the geomorphic indices and Iat

Class Geomorphic indices (Scored numbers in sub-basins) Tectonic activity

Sl Af Bs Hi Vf Smf Class Grade

1 3 3 7 * * 9 1 High

2 1 8 3 1 1 5 13 Moderate

3 14 7 8 17 17 2 4 Low

Total 18 18 18 18 18 16** 18

*No class exists

**No Mountain front exist in 2 sub-basins

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occur, especially inHi andVf values (Table 2). All the

sub-basins have the same class in both indices; Class 3,

except Sub-basin No. 11 and 10, respectively which

have Class 2 (Table 2). These exceptional values do

not influence significantly on the average results of the

acquired values.

The Af, Bs and Smf indices are distributed over the

three main classes of El-Hamdouni et al. (2008)

(Table 2).This is attributed to: (1) Locally, hard and

massive beds of conglomerate and/or sandstone may

influence on the shape of the valleys and their width

and depths; accordingly, different results are acquired

at different parts in the same sub-basins, (2) The dip

amount of the exposed rocks may also influence on the

symmetry of the valleys, especially when a valley runs

parallel to the main strike of the exposed rocks, the

exposed rocks on both sides may have different dip

amounts; accordingly, the valley will show different

symmetry, and (3) Locally, soft and thick claystone

beds, especially in the Bai Hassan Formation will

exhibit flat or gently sloping areas within a certain sub-

basin; accordingly, the acquired values will differ

from the acquired values of other indices. The values

of Sl index are also distributed over the classes with

the majority being of Class 3 (Table 2), which means

Low tectonic activity. This can be attributed to the

prevailing of the clastic rocks in the sub-basins;

therefore, the grade and rate of the weathering and

erosion will be almost the same. Accordingly, the ratio

of the valley length to its width will be almost the

same; with few exceptions due to the presence of

different rock types; rather than the clastics.

7 Conclusions

The Kifri Chai Basin is divided into eighteen sub-

basins depending on the 4th, 5th and 6th stream orders

to indicate the tectonic activity in the main basin. The

tectonic activity is acquired by indicating the six

geomorphologic indices that lead to the value of the

tectonic activity (Iat). To indicate the values of the six

indices, the required data were measured at each sub-

basin using ArcGIS technique, the numerical data is

acquired from the DEM.

The tectonic activity of each sub-basin is indicated;

accordingly, the average tectonic activity of the Kifri

Chai Basin is indicated. A Moderate tectonic activity

is assigned to the Kifri Chai Basin; because the

average Iat value is found to be 2.35, which assigns to

Class 3 and means Moderate tectonic activity.

The regional Neotectonic activity is compared with

the relative tectonic activities in the eighteen sub-

basins. Generally, there is a fair relation between the

two comparatives; especially the subsidence amounts

and the scored relative tectonic activity value (Iat),

especially, when the range of the subsidence in a

certain sub-basin is high.

Acknowledgements The authors express their sincere thanks to

Iraq Geological Survey (GEOSURV, Iraq) for submitting relevant

data which were used in the current research work. Moreover, for

supplying satellite and images and geological maps. Thanks are

extended toDr. ArsalanO. Al-Jaf (GEOSURV, Iraq) for his critical

discussions which amended the manuscript.

Open Access This article is distributed under the terms of the

Creative Commons Attribution 4.0 International License (http://

creativecommons.org/licenses/by/4.0/), which permits unrest-

ricted use, distribution, and reproduction in any medium, pro-

vided you give appropriate credit to the original author(s) and

the source, provide a link to the Creative Commons license, and

indicate if changes were made.

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